Evolution of Vitrinite Ultrafine Structures During ... - ACS Publications

Chapter 12

Evolution of Vitrinite Ultrafine Structures During Artificial Thermal Maturation 1

1

2

3

F. Laggoun-Défarge , E . Lallier-Vergès , I. Suárez-Ruiz , Ν. Cohaut , Α. Jiménez Bautista , P. Landais , and J. G. Prado 2

4

2

Downloaded by COLUMBIA UNIV on September 4, 2012 | http://pubs.acs.org Publication Date: November 9, 1994 | doi: 10.1021/bk-1994-0570.ch012

1

2

Unité de Recherche en Pétrologie Organique, Unité de Recherche Associée, 724 du Centre National de la Recherche Scientifique, Université d'Orléans, 45067 Orléans, Cedex 2, France Instituto Nacional del Carbón (CSIC), L a Corredoria, s/n. Apartado 73, 33080 Oviedo, Spain Centre de Recherche sur la Matière Divisée, Unité de Marine Recherche, 0131 du Centre National de la Recherche Scientifique, Université d'Orléans, 45067 Orléans, Cedex 2, France Centre de Recherche sur la Géologie de l'Uranium, B P 23, 54501 Vandœuvre-lès-Nancy Cedex, France 3

4

Simulation of the natural coalification of a low-rank pure vitrinite (Rm=0.5%) was performed in a confined-pyrolysis system. Vitriniteloaded gold tubes were isothermally heated at different temperatures (300 to 450ºC) during 72 hours at a constant pressure (70 MPa). At the end of each pyrolysis run, vitrinite samples were analyzed using reflectometry, Rock-Eval pyrolysis, X-ray diffraction and principally transmission electron microscopy (TEM). T E M investigations of ultra-thin sections show that thermal degradation initially affects the homogeneous vitrinite relative to cell walls which are more resistant. This degradation starts at 320ºC with fracturing and the appearance of uranium aggregates systematically associated with degraded vitrinite. The peak of the plastic phase is reached at 340ºC, corresponding to maximum hydrocarbon generation (extract yield = 9.3%). Botanical structures identified in the initial sample disappear at 380ºC. No organisation of the basic structural units has been noticed even at 450ºC. Vitrinites are the major pétrographie components of most coals, and thus contribute significandy to their industrial properties. Coal petrography classically describes some major types of vitrinites, essentially based on their morphological properties observed in light microscopy. Due to the limited resolution of these optical methods, the ultrafine structures of vitrinites (porosity, mineral inclusions, vegetal structures...) are not yet well defined. However, some recent studies using electron microscopy have been conducted on the main types of macérais in order to define their composition and textural aspect (1-6 ). This study addresses this problem and has two main aims. The first is to investigate the ultrafine structures of a low-rank, pure vitrinite. This vitrinite was hand-picked in large quantities from the same layer, which allowed a suite of different analyses to be performed. The second is to characterize the behaviour of vitrinite, and more precisely to follow the evolution of its fine and ultrafme structures during thermal maturation. Due to the difficulty of sampling a complete and 0097-6156/94/0570-0194$08.00/0 © 1994 American Chemical Society

In Vitrinite Reflectance as a Maturity Parameter; Mukhopadhyay, P., et al.; ACS Symposium Series; American Chemical Society: Washington, DC, 1994.

12. LAGGOUN-DEFARGE ET AL.

Evolution of Vitrinite Ultrafine Structures

195

homogeneous natural maturation series of coals, an experimental simulation of natural coalification was used (confined pyrolysis) which has been shown to reproduce natural maturation (7, 8 ).


Sampling, Preparation Methods and Analytical Techniques A vitrinite sample was selected by hand-picking from a Stephanian high-volatile bituminous coal. This sample comes from the uppermost seam of the open pit mine named Fouthiaux in the Montceau-les-Mines Basin in France. The choice of this vitrinite was based on its homogeneity in light microscopy, its low mineral content and its relative immaturity. Artificial maturation of this vitrinite was carried out in a confined pyrolysis system. 300 mg of a powdered sample were placed under argon atmosphere inside a sealed gold tube which was introduced into a cold-seal autoclave. The standard conditions of heat treatment used were, a 72 hour isothermal stage, temperatures of 300, 320, 340, 380, 400 and 450 C, and a constant pressure of 70 MPa which was exerted on the tube in order to ensure a confinement (9,10 ). Both the raw vitrinite and pyrolized samples were studied on polished sections and/or embedded grain sections by light microscopy (reflected light and under U V excitation). Additional aliquots were ground in order to be studied by Rock-Eval pyrolysis, X-ray diffraction, scanning electron microscopy (SEM) and finally, transmission electron microscopy (TEM). T E M observations were performed on ultra-thin sections using a S T E M Philips CM-20 instrument. Elemental microanalyses were obtained using an energy dispersive X-ray (EDX) spectrometer fitted to the STEM CM-20. The ultrathin sections (30 to 50 nm thick), which were cut using a diamond knife, from grains embedded in a methylmetacrylate resin (77 ), were placed on perforated carbon filmed grids. The pyramid plane surfaces, from which ultrathin sections had been made, were observed by optical microscopy and by S E M , in order to compare these observations with those of the TEM. The X-Ray Diffraction (XRD) apparatus consists of a transmission diffractometer using Κι α molybdenum radiation, equipped with a curve localization detector connected to a multichannel analyser. Relative intensities are expressed in arbitrary units. It is from the (002) reflection, which is due to the periodic stacking of aromatic layers, that the following parameters are calculated: (1) doo2 which represents the mean interlayer spacing of aromatic sheets: g

2 ά(χ)2 sin θ = λ λ = 0.709 Â (wave length for Molybdenum radiation) (2) L which is the stack height of aromatic layers deduced from the Scherrer formula: c

L = 0.89/cos θ Δ (2 θ) c

(3) which is the averaged number of aromatic layers: = L / d o o 2 c

The (10) band, which corresponds to the extension of aromatic molecules in the plane of the layer, has also been studied. Results and Discussion Petrographical and Geochemical characteristics. The raw vitrinite is composed of 97 vol. % telocollinite and humotelinite and is relatively immature (Rm = In Vitrinite Reflectance as a Maturity Parameter; Mukhopadhyay, P., et al.; ACS Symposium Series; American Chemical Society: Washington, DC, 1994.

196

VITRINITE REFLECTANCE AS A MATURITY PARAMETER 9

0.5% and Rock-Eval pyrolysis Tmax = 438 C). The hydrogen index (HI), about 104 mg HC/g C org. (Table I), is typical of type ΠΙ organic matter. Both reflectance and Rock-Eval pyrolysis Tmax increase as confined pyrolysis temperature (P. T.) increases during maturation, up to 2.7% for Rm and 590*C for Tmax at 4 5 0 ^ P. T. (Table I). Conversely, the HI decreases to 9 mg HC/g C org. at this pyrolysis temperature.


Table I. Reflectance and Geochemical Parameters of the Raw and Pyrolyzed Samples Samples raw 300*0 320=0 340*0 380*0 400 C 450 C

Rm(%) 0.53 0.95 1.18 1.51 2.02 2.19 2.71

a

2

Tmax CO) 438 467 479 495 549 568 590

HI(mgHC/gCorg) 104 87 83 69 57 24 8

CHCI3 extract (%) — 1.76 5.08 9.30 1.07 0.90 0

Unlike natural series, the artificially maturated vitrinites studied do not exhibit any anisotropy in polarized light. This is probably due to the multidirectional pressure exerted during the confined pyrolysis. Evolution of Physical Structure. The evolution of physical structure of the carbonaceous matter has been followed during the artificial maturation by X R D study. The diffractograms of the raw vitrinite, as well as those of the 340 and 450PC stages, are presented in figure 1 and the structural parameters, calculated from the (002) reflection, are summarized in table Π. The X R D results do not reveal any mineral phases in the vitrinite. The carbonaceous matter of the raw sample is poorly organized with a weak (002) reflection and no (10) band (Figure 1). The critical stages in the organization of the carbonaceous matter are 340 and 450 C. A t 3 4 0 ^ , the (002) reflection is more prominent (Figure 1). A n even higher degree of organization of turbostratic layers is observed at the 450 C stage, as the (002) reflection becomes sharper and shifts to higher angles. In addition, the (10) band becomes more evident at 450 C, which means that the size of basic structural units is increasing (Figure 1). The mean interlaver spacing of aromatic sheets (0002) decreases from 3.65 Â in the raw sample to 3.54 A at the 4 5 0 ^ stage (Table i p . Conversely, the mean stacking size of aromatic layers (L ) and their number () increase respectively from 11.5 A and 3 in the raw sample, to 28 Â and 8 at the 4 5 0 ^ stage (Table Π). Q

Q

9

c

Table II. Structural Parameters of the Carbonaceous Matter Calculated from X-ray Diffraction Data Samples raw 34(FC 380*C 450 C Q

d(X)2 (Â) 3.65 3.58 3.55 3.54

L (A) C

11.5 21.4 24.5 28

3 6 7 8

These results are interpreted as a separation of volatile aliphatic hydrocarbons at 340 C. This is confirmed by the chloroform extraction results which show that 2




12. IAGGOUN-DEFARGE ET AL.


197

198

VITRINITE REFLECTANCE AS A MATURITY PARAMETER

maximum hydrocarbon generation (extract yield = 9.3%) is acheived at this temperature. A n even greater aromatization of the carbonaceous matter is attained at 450 C.


Q

Evolution of Ultrafine Structure. While the observations in light microscopy have shown that the raw vitrinite is homogeneous and amorphous (Figure 2), the T E M investigations reveal several structures which take the form of sinuous, continuous laminae, denser (more opaque to electrons) than the surrounding material (Figure 3). They have been considered as indicating the presence of vegetal cell walls (5 ). The latter delimit the cellular cavities which are filled with an amorphous matrix of variable porosity (see A and Β in Figure 3). Therefore, the differences observed between cell walls and cavities underline the variability of the botanical origin, while the textural variations between the matrices might illustrate differences in the early gelification processes. The evolution of the fine and ultrafme structure of this vitrinite during artificial coalification was studied by both S E M and T E M . At 300 C, the change in the structure is not substantial. However, at 320 C, the S E M observations show that the sample is more fractured with a porosity ranging from 1 to 10 μπι. Several "melted-forms" appear, probably indicating primary hydrocarbon generation. T E M investigations reveal that vegetal structures are still present (see cw in Figure 4). However, the amorphous matrices described above (see m in Figure 4) are more porous and consist of a granular matter exhibiting polygonal structures (Figure 5). This degraded material typically has pore sizes ranging from a few Angtroms to 0.2 μπι. Therefore, this granular ultrastructure associated with the fracturing is probably the result of thermal degradation, which mostly affects the massive matrix, rather than the more resistant cell walls. Opaque grains measuring between 10 and 50 Â (Figure 6) are systematically associated with the polygonal structures described above. These grains were identified by E D X analysis as uranium inclusions (see inset in Figure 6). These inclusions, being probably in the form of organo-uranyl complexes (12 ), were not detected in the raw vitrinite. Due to the effect of temperature, the transformation of these complexes lead to a breakage of organo-metallic cross-linkages, followed by a formation of uraninite crystals ( 13 ). Indeed, it has been demonstrated that alcoholic and aliphatic hydrocarbon groups in the organic matter are generally responsible for this reduction (14 ). This reduced uranium may be thus expelled and preferentially concentrated in the zones of vitrinite degradation; i.e., in the granular phase described above. At 340 C, devolatilization vacuoles and matrix "melted-forms" appear in large quantity (Figure 7). They certainly indicate the maximum of the plastic phase and thus the peak of hydrocarbon generation, which is confirmed by the chloroform extraction results as discussed above. At 380 C, the botanical structures observed below this temperature disappear. The uraninite crystals are well-shaped, often aggregated (see ua in Figure 8) and systematically associated with the vacuoles. At this temperature, these crystals are larger in size (200 to 500 Â). A selected-area electron diffraction (SAD) pattern was obtained (see inset in Figure 8) and enabled the identification of uraninite crystals. At 400 C, no substantial evolution of the ultrafine structure is noticed. However, A t 450 C, S E M observations show that the devolatilization vacuoles have spread and coalesced (Figure 9). Most of these vacuoles were sealed by thin skins which often appear broken, probably due to sudden gas expulsion. This gas production-expulsion phenomenon seems to occur in successive stages as seen in Figure 10. Furthermore, T E M investigations using point high resolution show that the ultrafine structure of vitrinite (see ν in Figure 11) is still "amorphous" and does not reveal any organisation of basic structural units, even near the rare minerals (clays ) detected at this temperature (see c in Figure 11), despite their demonstrated catalytic 2

9

S

S

fi

S





Figure 2: The raw vitrinite observed by reflected light microscopy, oil immersion.

Figure 3: T E M micrograph of the raw vitrinite showing vegetal cell walls (cw) which delimit cellular cavities filled with amorphous matrices of variable porosity (AandB).


199


200


Figure 4: T E M micrograph of the vitrinite pyrolized at 3 2 0 ^ showing that the thermal degradation affects essentially the massive matrices (m) compared to the more resistant cell walls (cw).

Figure 5: Detail of the thermally degraded material which exhibits a granular structure intimately mixed with more opaque uranium granules.





201

Figure 6: High resolution T E M micrograph of the opaque uranium granules (ug) identified in the X-ray spectrum (see inset).

Figure 7: T E M micrograph of devolatilization vacuoles of the vitrinite pyrolyzed at 340*0. In Vitrinite Reflectance as a Maturity Parameter; Mukhopadhyay, P., et al.; ACS Symposium Series; American Chemical Society: Washington, DC, 1994.


202


Figure 8: T E M micrograph of uranium aggregates (ua) associated with the devolatilization vacuoles in the vitrinite pyrolyzed at and selected-area electron diffraction (SAD) pattern of these aggregates (see inset).

9

Figure 9: S E M micrograph of the vitrinite maturated at 450 C showing the generalization of coalescent devolatilization vacuoles.





203

Figure 10: A devolatilization vacuole with two thin broken skins indicating, (1): a sudden gas expulsion, (2): two successive stages of this gas productionexpulsion phenomenon.

Figure 11 : High resolution T E M micrograph or the caroonaceous matter of the vitrinite (v) pyrolyzed at 450 C and its selected-area electron diffraction (SAD) pattern (see inset). This vitrinite is associated with clays (c). Q


204


effect. This is indeed supported by the carbonaceous matter SAD pattern which exhibits a very weak (10) reflection (see inset in Figure 11).


Conclusions Electron microscope investigations complemented principally by X-ray diffraction provided furthur information about the ultrafine structure of vitrinites, thus enabling a better understanding of their behaviour during artificial thermal maturation. Raw vitrinite, which appears completely homogeneous under the light microscope, has been shown by T E M observations, to possess botanical structures. These structures take the form of cell walls delimiting cavities full of amorphous matrices which present different porosities. This was interpreted as a selective preservation of the cell walls, and as differences in the early gelification processes concerning the matrices. During artificial coalification, it has been shown that thermal degradation begins at 320 C and mostly affects the massive matrices compared to the more resistant cell walls. This degraded vitrinite exhibits a granulous texture and is systematically associated with uranium granules ranging from 10 to 50 Â in size. These inclusions, which are not detected in the raw vitrinite, probably result from breakage of organo-metallic cross-linkages and a formation of uraninite crystals, which are then preferentially concentrated in the zones of vitrinite degradation. This study shows that the maximum of hydrocarbon generation is reached at 340 C, as indicated by the chloroform extraction results and confirmed by the apppearance of devolatilization vacuoles in T E M . The botanical structures disappear completly at 380 C, replaced by an extensive development of vacuoles which are associated with uraninite aggregates. Finally, even at 450 C the ultrafine texture of vitrinite does not exhibit any molecular orientation domains at high resolution, and remains as poorly organized elementary carbonaceous granulations. However, the X-ray diffraction study shows that the degree of organization of the carbonaceous matter in turbostratic layers increases (Lc = 28 À against 11.5 Â in the raw vitrinite). This is probably due to the fact that the lateral organization of the basic structural units is not sufficiently developped to be detected by TEM-high resolution. 9

9

9

2

Acknowledgments We are indebted to the European Community, program n° 7220-EC-757 for financial support. We thank A . Genty from the "Ecole Supérieure de l'Energie et des Matériaux", Orléans, and C. Clinard from the "Centre de Nanoscopie Analytique", Orléans, for their technical assistance, and also acknowledge S. Bonnamy and F. Lambert from the "Centre de Recherche sur la Matière Divisée", Orléans, for the ultramicrotom facilities. M . Boussafir, G . Drouet, E . Jolivet and A . Patience are gratefully acknowledged for their assistance in the preparation of the manuscript. Literature Cited 1. Harris, L.A.; Yust, C.S. In : Coal structure, Am. Chem. Soc. 1981, pp.321-336. 2. Lallier-Vergès, E.; Bertrand, P.; Guet, J.M.; Clinard, C.; Lin, Q.; Wu, X.Q. Bull. Soc. géol. France 1991, 162, pp.163-174. 3. McCartney, C.T.; O'Donnell, H.J.; Ergun, S. "Coal Science", Adv. Chem. ser. 1966, 55, pp.261-273. 4. Taylor, G.H. "Coal Science", Adv. Chem. ser. 1966, 55 pp.274-283. 5. Taylor, G.H.; Shibaoka, M . ; Liu, S. Fuel 1982, 61, pp.1197-1200. 6. Taylor, G.H.; Teichmuller, M . Int. J. Coal Geol. 1993, 22, pp.61-82. 7. Monthioux, M . ; Landais, P.; Monin, J.-C. Org. Geochem. 1985, 8, pp.275-492.


12.

LAGGOUN-DEFARGE ET AL.


205


8. Landais, P.; Zaugg, P.; Monin, J.-C.; Kister J.; Muller, J.-F. Bull. Soc. géol. Fr. 1991, 162, pp.211-217. 9. Landais, P.; Michels, R.; Poty, B. J. Anal. Appl. Pyr. 1989, 16, pp.103-115. 10. Landais, P.; Michels, R.; Kister, J.; Dereppe, J.-M.; Benkhedda, Z. Energy & Fuels 1991, 5, pp.860-866 11. Tchoubar, C.; Rautureau, M . ; Clinard, C.; Ragot, J.-P. J. Microscopie 1973, 6, pp.147-154. 12. Disnar, J.-R.; Trichet, J. C. R. Acad. Sc. Paris. 1983, 296, pp.631-634. 13. Meunier, J.-D.; Landais, P.; Pagel, M . Geochem. Cosmochim. Acta 1990, 54, pp.809-817. 14. Nakashima, S.; Disnar, J.-R.; Perruchot, Α.; Trichet, J. Bull. Minéral. 1987, 770, pp.227-234. RECEIVED April 15, 1994


Evolution of Vitrinite Ultrafine Structures During ... - ACS Publications

Recommend Documents